1. IntroductIon

The stratigraphic succession exposed in the Gebel Hafit area of the United Arab Emirates (Fig. 1) ranges from Eocene to Miocene in age (HUnTinG, 1979; CHERiF & El DEEb, 1984; HAMDAn & bAHR, 1992; AnAn et al., 1992; AnAn, 1996). basically, the lower Eocene is represented by a relatively thin sequence of lime-stones, with marl intercalations in its upper part (Rus Formation), while the Middle and Upper Eocene are represented by thick sequences of limestones with marl and shale intercalations (Dammam Formation). both formations have a wide aerial extent in the Emirates, Qatar, and Saudi Arabia (boUkHARy & Al SHAR-HAn, 1998).

2. StratIgraphy

The stratigraphic section measured along Wadi Tarabat at the core of the Hafit domal structure (Fig. 2) is repre-sented by two formations, an older Rus Formation and younger Wadi Al nahayan Formation.

Somalina praestefaninii n.sp., a new Species of Large Foraminifera from the dammam Formation (Lutetian) of gebel hafit, united arab Emirates

Mohamed Boukhary1, Danielle dEcrouEz2 and Yasser A. EL SaForI1

2.1. rus Formation, Late ypresian

The Rus Formation (THRAllS & HASSon, 1956) is composed of 40 m of white, medium to coarse grained, thickly bedded limestone, with gray chert nodules in the lower part and marl intercalations in the upper part. Two members are distinguished within the Rus Forma-tion, the Sulaimi and Doha Members.

2.1.1. Sulaimi Member

The Sulaimi Member (boUkHARy & Al SHAR-HAn, 1998) is exposed in the lower part of Gebel Hafit and is composed of about 25 m of thick-bedded white or cream-weathering medium to coarse-grained lime-stone. The upper part is composed of thinly-bedded cream to light-brown argillaceous limestone. The base of this unit is not exposed. based on foraminifera Aca­rinina bullbrooki bolli, Globigerina turgida FinlAy, and Morozovella aragonensis (nUTTAll), the unit is assigned to the level of the late Early Eocene. The middle part is either barren or with poorly preserved foraminifera, such as Acarinina bullbrooki bolli, A. pentacamerata SUbboTinA, Globigerina turgida FinlAy, Morozovella aragonensis (nUTTAll), and is characterized by a nummulitic horizon with Nummu­lites subramondi DE lA HARpE, besides Orbitolites, Alveolina and algal nummulitic limestones. This unit is correlated with the middle part of the Hili Member of the Rus Formation according to HAMDAn & bAHR (1992). The upper part is conformable with the overly-ing Doha Member.

2.1.2. Doha Member

The Doha Member (boUkHARy & Al SHARHAn, 1998) is defined from the lower Eocene outcrops of Qatar. it is unconformably overlain by the Dammam Formation (as defined from Qatar). The unit is com-posed of well-bedded grey to cream, fine–medium-grained nodular limestones with chert nodules and marl intercalations (15 m). Marls are rich in plank-tonic foraminifera, including Subbotina inaequispira (SUbboTinA), Globigerina turgida FinlAy, Moro­zovella aragonensis (nUTTAll), M. lensiformis SUb-boTinA, M. quetra bolli, Acarinina broedermanni CUSHMAn & bERMUDEz, A. bullbrooki bolli, A. pentacamerata SUbboTinA, A. pseudotopilensis (SUbboTinA), A. triplex SUbboTinA, A. solda­

GeologiaCroatica 59/2 99–107 4 Figs. 1 Pl. ZAGREB 2006

key words: Somalina, Taxonomy, Eocene, United Arab Emirates.

1 Ain Shams University, Faculty of Science, Geology Department, Abbassia 11566, Cairo, Egypt; e-mail: moboukhary@yahoo.com

2 Muséum d’histoire naturelle de Genève, 1, Route de Malagnou, CH-1208 Genève, Suisse

abstractThe nodular limestones exposed at the basal part of the Gebel Hafit (United Arab Emirates) represent a truncation surface, between the Rus and the Middle Eocene Dammam Formation (Mibazara Mem­ber). Somalina praestefaninii n.sp. is a new large foraminiferal spe-cies separated from the Mibazara member. it is believed that Soma­lina praestefaninii n.sp. is the ancestral form of Somalina stefaninii SilvESTRi as it is smaller and has a more simple protoconch. Here, it is believed that the taxon Somalina (lutetian) could possibly be derived from Opertorbitolites nUTTAll, 1925 (the taxon character-istic for the ypresian).

100 Geologia Croatica 59/2

doensis SUbboTinA, A. spinuloinflata bAnDy, and Pseudohastigerina micra (ColE). Some horizons are rich in large foraminifera, e.g. Nummulites bassiounii boUkHARy & blonDEAU. According to the fora-miniferal associations this unit is dated as late Early Eocene (boUkHARy & blonDEAU, 1991). The unit is correlated with the upper part of the Hili Member of HAMDAn & bAHR (1992).

2.2. Wadi al nahayan Formation, Early/Middle Lutetian

The Wadi Al nahayan Formation (HAMDAn & bAHR, 1992) forms the basal part of the El Dammam

Group. it is composed of tan to light brown limestone with shale interbeds. The Dammam Group (720 m thick) is separated into four formations from base to top: Wadi Al nahayan, Ain Al Faydah, Maziad, and Senaiya Formations. The Wadi Al nahayan Formation is separated from the underlying Rus Formation by a 6 m thick conglomeratic layer, the Mibazara Member (boUkHARy et al., 2006). This unit is composed of highly compacted and unoriented limestones pebbles and cobbles. The clasts are highly cemented by a fine reddish matrix of marly nummulitic carbonates rich in large benthic foraminifera, including Assilina spira abrardi SCHAUb, Somalina praestefaninii n.sp., and Nummulites perplexus SCHAUb, similar to the basal

U. Eocene

Maziad Fm. (M. Eocene)

Fig. 1 Location map of the Gebel Hafit area (after CHERIF & EL DEEB, 1984).

101Boukhary, Decrouez & El Safori: Somalina praestefaninii n.sp. ...

lutetian assemblage of italy (SCHAUb, 1981, p. 132). The unit is exposed on both limbs of the Hafit anticline with a variable thickness (3–6 m). These conglomerates represent a sudden shallow shift in sedimentation rela-ted to an uplift of the Arabia platform during the Early to Middle lutetian. Also, this uplift seems to be respon-sible for the absence of the p10–p12 interval on the western side of Qatar (lutetian lacuna, boUkHARy & Al SHARHAn, 1998).

2.3. Stratigraphic remarks

The studied section is correlated with other countries (Qatar, Saudi Arabia and Egypt) to delineate important

stratigraphic levels related to Somalina occurrences (Fig. 3). Consequently, Somalina praestefaninii n. sp. recorded from the basal part of the Dammam Fomation (lutetian) is the ancestral form of Somalina stefaninii SilvESTRi, a characteristic species for the bartonian. Also, the sequence of Somalina praestefaninii n. sp. could be correlated with the stratigraphic lacuna (between the Rus and Dammam formations) in Qatar, bahrain, kuwait, Saudi Arabia and Egypt (boU-kHARy & Al SHARHAn, 1998; boUkHARy et al., 2006). Accordingly, the Mibazara Member corresponds to the black and red tuffs with Nummulites perplexus of Malo, italy (SCHAUb, 1981), where both of the two units are characterized by conglomeratic facies.

-

-

Fig. 2 Stratigraphy of the Ear-ly–Middle Eocene outcrop section in the Hafit area.

102 Geologia Croatica 59/2

Also, Somalina hottingeri WHiTE may be related to Somalina praestefaninii n.sp. According to the known global sequences, four major (2nd order) stratigraphic sequences are recorded as follows.

1 – Umm Er Radhuma–Rus Sequence (Ypresian,TA–2): Umm Er Radhuma–Rus/Esna Thebes–Minia Formations.This sequence is represented by a succession of shales and limestones and laid down under a major Tethyan transgression. The sequence ended with a major regression resulting in the absence of Early

lutetian deposits in many parts of the Arabian plate (boUkHARy & Al SHARHAn, 1998).

2 – WadiAlNahayan–AinAlFaidaSequence(Lute­tian,Early–MiddleTA3): Wadi Al nahayan–Ain Al Faida / Samalut–Maghagha–Qarara Formations.This sequence is represented by a succession of marls and limestones and was laid down under a major Tethyan regression accompanied by the Middle Eocene hyperthermal event (SCHMiDT & SHinDEll, 2003). This sequence is only recorded from the United Arab Emirates and Egypt. A tectonic trigger for this sequence is obvious from the lower Egyptian basins (Mokattam).

LithostratigraphySequencestratigraphy

Egypt

Somalinasp.

evolutionSaudi ArabiaQatar

MokattamNileValley

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an

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ibon

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DukhanMb.

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Som

alin

aste

fani

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Dam

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MidraMb./

Saila Mb.

Dam

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UpperBuilding

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atta

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.

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iad

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toni

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izeh

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ara

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.

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UmmRadhuma

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up

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Fig. 3 A proposed stratigraphic clas-sification and correlation of the Eocene sequen-ces in the United Arab Emirates, and the Somalina evolution trend. Grey areas are unconformities.

103Boukhary, Decrouez & El Safori: Somalina praestefaninii n.sp. ...

3 – MaziadSequence(Bartonian,LateTA3): Mazi-ad / Mokattam–Fashn / Dammam Formations.This sequence is represented by limestones deposited under a major transgression of Tethys. The sea level rise may have led to the evolution of Somalina stefaninii SilvESTRi across broad extents of the Arabian and African plates. The sequence has a wide distribution in the various Arabian countries.

4 – Senaiya Sequence (Early Priabonian, TA4):Senaiya / Schaibon Formations.This sequence is represented by a succession of marl and limestone and was laid down under a major regression of Tethys which led to the absence of Early priabonian sediments in many parts of the Arabian plate. like the Wadi Al nahian–Ain Al Faida Sequence, this sequence is only recorded from the United Arab Emirates and Egypt.

3. SyStEMatIc paLaEontoLogy

Classification: following loEbliCH & TAppAn (1988)

Suborder: Miliolina DElAGE & HERoUARD, 1896

Superfamily: Soritacea EHREnbERG, 1839

Family: Soritidae EHREnbERG, 1839

Genus: Somalina SilvESTRi, 1939

The genus Somalina, considered as monospecific, was first figured by SilvESTRi (1938) and described by himself in 1939 from the lower Eocene of Somalia and Egypt. in 1948, he mentioned and illustrated for the second time, new specimens provided from Egypt (Geb-el Ataka, Collection of J. Cuvillier) of lower Eocene age. HEnSon (1948) erected from the lutetian of iraq and oman the species S. danieli HEnSon (S. danieli sp.nov., p. 60, pl. 3, figs. 2–3, HEnSon, 1950). Hen-son’s illustrated thin sections are oblique sections and the only difference, given by this author, from the type species is by that it has a “smooth” or only slightly pit-ted surface. HEnSon (1950) also mentioned from the Upper Eocene of iraq Somalina danieli sp. nov. var.? (p. 61, pl. 3. figs. 4–6). The difference from the type spe-cies is “... a marked inflation of the test at the poles and an exceptionally large, irregular, multicellular, mega-lospheric embryo ranging in diameter from 0.3 mm to over 2 mm”. Henson justified this separation mainly on the younger age of this form, because he admitted that the criteria for its separation are not particularly signifi-cant. AzzARoli (1952) described and again illustrated S. stefaninii SilvESTRi from the ledian of Somalia (in the lower part of the Carcar iv) with Linderina buranen­sis nUTTAll & bRiGHTon, Pentellina sp., rotalids and miliolids. RAHAGHi (1978) described Somalina stefaninii SilvESTRi from the Middle Eocene of iran (region of Shiraz), the diameter of these specimens is

8 mm and their thickness is 1.6 mm. The embryonic apparatus has an internal dimension (in vertical section) of 600x400 μm. This species is associated with Pseudo­lituolinella reicheli MARiE, Lituonella sp., Dictyoconus sp., Praerhapydionina sp., and Orbitolites complanatus lAMARCk. Also, this author described two new spe-cies: Somalina gigantea RAHAGHi and S. khorassani­ca RAHAGHi, both from the Middle Eocene. S. gigan­tea RAHAGHi 1978 (pl. 3, figs. 1–3; pl. 4, figs. 1–3; pl. 41) has a diameter of 3.7 mm and a thickness of 0.4 mm for the forma A with a plurilocular apparatus in verti-cal section, with internal dimension of 1200x500 μm. For the forma b, the diameter is 33 mm for a thickness of 3 mm. The lateral layers, with vacuoles of variable dimensions, are similar to those of the type species. The new species mainly differs from the other species by its shape and size. it is associated with Alveolina aff. muni­eri HoTTinGER and Alveolina sp. only the form A of S. khorassanica RAHAGHi is known (RAHAGHi, 1978, p. 41–42, pl. 2, fig. 4). The main characteristic of this form is the reduction and even the absence of the lateral layers. its diameter is 0.7 mm and can reach 8 mm. The embryonic apparatus has an internal dimen-sion of 300x400 μm. It is associated with Alveolina sp. and Rotalia sp. These characteristics, in our opinion, are not sufficient to nominate a new species. However, it is impossible to have a definite opinion on this matter before examining the samples. it should be, neverthe-less, noticed that Rahaghi must have had an extremely rich collection, which explains the great diversity he was able to observe. He again mentions these species in his later work (RAHAGHi, 1980). bEUn (1982) men-tioned S. stefaninii SilvESTRi from the lower Eocene of SE Afghanistan, accompanied by Assilina spinosa DAviES, and A. placentula DESHAyES. kAEvER (1970) recorded Somalina stefaninii SilvESTRi from the Middle Eocene of Afghanistan. kURESHi (1969, 1972) mentioned S. stefaninii SilvESTRi from the lower Eocene of western pakistan. FoRTElEoni & RADRizzAni (1972) recorded S. stefaninii SilvES-TRi from the Middle Eocene of Somalia (pl. v, fig. 1) with Lockhartia haimei (DAviS), Rotalia sp., Dendriti­na sp. and miliolidae. SAMpo (1969) mentioned Soma­lina stefaninii SilvESTRi (pl. 39 – middle Eocene and pl. 45 – ”Jahrum Formation”) from iran. JAMES & WynD (1965) illustrated Somalina sp. from the “Jah-rum Formation” of iran (fig. 66). lEHMAnn (1961) renewed the description of the species after examining specimens from Egypt and iran. However, the author noticed that the forms from iran are larger than those from Egypt. Stratigraphically, lehmann considered Somalina as a foraminifera of the lutetian (p. 660–663, figs. 47–49, tab. 14, figs. 4 & 5). WHiTE (1997) described Somalina hottingeri WHiTE with partially vacuolate lateral walls from Wadi Fatah, oman, Arabian Gulf. SHAMAH & HElAl (1994) recorded Somalina stefaninii SilvESTRi from an Eocene hill south west Gebel El Goza El Hamra, Shabrawet area, Cairo–Suez district, Egypt.

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Depository: All types are deposited in the collection of Mohamed boukhary, Department of Geology, Faculty of Science, Ain Shams University, Cairo, Egypt.

Somalina praestefaninii n.sp.(pl. 1, Figs. 1–13)

Etymology: prior to Somalina stefaninii SilvESTRi in age.

Holotype: pl. 1, Fig. 13, Sample no. sh. 17b.

Paratypes: 7 microspheric individuals and 2 megalo-spheric individuals in thin sections.

Locus Typicus: Gebel Hafit, Wadi Tarabat (lat. 24°02’n and long. 55°54’E).

Stratum typicum: Conglomeratic limestone with boulders and fragments containing N. bassiounii boUkHARy & blonDEAU and reddish matrix with Assilina spira abrardi SCHAUb, Early lutetian (Wadi Al nahayan Formation, Mibazara Member, Gebel Hafit), sample no. sh. 17b.

Diagnosis: Somalina praestefaninii n. sp. is believed to be the ancestral form of Somalina stefaninii SilvESTRi. it differs from Somalina stefaninii SilvESTRi by being smaller in size, with a smaller protoconch, and a less complicated embryonic chamber. instead of having a wrinkled protoconch as in the case of Somalina stefaninii SilvESTRi, the protoconch of Somalina praestefaninii n. sp. is partially divided by a simple loop (Fig. 4).

DescriptionMicrosphericform: Test of medium size, flat to lenticu-lar, sometimes compressed to extremely pointed at the peripheral margin, diameter 15–20 mm, thickness 2–4 mm, the test consists of median and lateral structures, chambers in the median part of cavities and the lateral chambers are arcuate, larger near the central area and smaller in the outer margin. Cavities of the median part are elongated. Stolon is represented by a fine passage

connecting the chamberlets. Aperture not possibly seen since all the material is embedded in hard limestones.Megalosphericform: Test relatively small, diameter 3–3.5 mm with an average thickness of 500 to 750 μm. protoconch rounded, rectangular to subrectangular, 250–500 μm. The protoconch appears to be occupied by a half circle ribbon, more simplified than that in Soma­lina stefaninii SilvESTRi, in which the protoconch is plurilocular.

acknowledgements

The authors wish to thank prof. Dr. Mohamed bASSio-Uni, Ain Shams University, and prof. Dr. bahay iSSA-Wi, former Director of the Egyptian Geological Survey for reviewing the manuscript. The authors are deeply grateful to prof. Dr. Hans-peter lUTERbACHER for his kind help in identifying planktonic foraminifera. Also, we are thankful to prof. Dr. Rajko pAvlovEC for his critical review of the manuscript.

4. rEFErEncES

AnAn, H.S. (1996): Early Eocene foraminifera of Jabal Hafit, United Arab Emirates.– M.E.R.C. Ain Shams Univ. Earth Sci. Ser., 10, 147–162.

AnAn, S.H., bAHR, S.A., bASSioUni, M.A., boUkHA-Ry, M.A.& HAMDAn, A.A. (1992): Contribution to early Eocene–oligocene biostratigraphy of Jabal Hafit succession, United Arab Emirates.– M.E.R.C. Ain Shams Univ. Earth Sci. Ser., 6, 225–247.

AzzARoli, A. (1952): i macroforaminifera della serie del Carcar in Somalia (Eocene medio e superiore) e la loro distribuzione.– palaontographia italica, 47, 99–131.

bEUn, n. (1982): Grands ensembles sédimentaires et struc-turaux des montagnes situées ă l’Est de la faille de Cha-man–Arghandeh, entre Ghazni et nopur (Afghanisstan du Sud–Est).– bull. Soc. Géol. France, 7(24)/2, 331–339.

boUkHARy, M. & Al SHARHAn, A.S. (1998): A stratigra-phic lacuna within the Eocene of Qatar: an example of the

Fig. 4 Protoconch characteristics of Soma-lina stefaninii SILvEStRI and Somalina praestefaninii n.sp.

105Boukhary, Decrouez & El Safori: Somalina praestefaninii n.sp. ...

interior platform of the Arabian peninsula.– Revue paléo-biol., Genève, 17/1, 49–68.

boUkHARy, M. & blonDEAU, A. (1991): Nummulites bassiounii n. sp. (N. perplexus lineage) of late Cuisian from beni Hassan, nile valley, Egypt.– n. Jh. Geol. palä-ont. Mh., 21–30.

boUkHARy, M., El SAFoRi, y.A., DECRoUEz, D. & FARiS, M.M. (2006): bio- and isotope stratigraphy of the lower/Middle Eocene section at Gebel Hafit area, United Arab Emirates.– n. Jh. Geol. palaont. Mh., 3, 129–147.

CHERiF, o.H. & El DEEb, W.M.z. (1984): The middle Eocene–oligocene of the northern Hafit area, South of Al Ain City (United Arab Emirates).– Géologie Méditerrané-ene, 11/2, 207–217.

FoRTElEoni, p.G. & RADRizzAni, G.p. (1972): Micro-faunes form the karka Formation (Somaliland).– Rev. Esp. Micropal. Serie 7, 3, 1975, proc. 5th African Colloq. Micropal., Addis Abeba, 10–12 Avril 1972, 385–415.

HAMDAn, A.R.A. & bAHR, S. (1992): lithostratigraphy of the paleogene succession of northern Jabal Hafit, Al Ain area, United Arab Emirates.– M.E.R.C. Ain Shams Univ. Earth Sci. Ser., 6, 201–224.

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HEnSon, F.R.S. (1950): Middle Eastern Tertiary peneropli-dae (foraminifera), with remarks on the phylogeny and taxonomy of the family.– Unpubl. phD Thesis, leiden (Wakefield), 70 p.

HUnTinG (1979): Report on mineral survey of the United Arab Emirates, Geology and mineral potential.– Hunting Geology and Geophysics ltd. Sponsored by petroleum & Mineral Resources, Abu Dhabi, 9, 1–29.

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kAEvER, M. (1970): Die alttertiären Grossforaminiferen Südost-Afghanistans unter besonderer berücksichtigung der nummulitiden. Morphologie, Taxonomie und biostra-tigraphie.– Munster. Forsch. Geol. paleont., H. 16, 400 p.

kURESHi, A.A. (1969): Eocene biostratigraphy of pakistan.– Mem. b.R.G.M., Coll. Sur l’Eocène, paris, Mai 1969, 69, 219–224.

kURESHi, A.A. (1972): The Cretaceous and Tertiary larger Foraminifera of West pakistan.– Rev. Esp. Micropal., 73, proc. of the 5th African Colloq. on Micropaleontology, 553–564.

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loEbliCH, A.R. & TAppAn, H. (1988): Foraminiferal genera and their classification.– nostrand Reinhold Com-pany, new york, 970 p.

RAHAGHi, A. (1978): paleogene biostratigraphy of some parts of iran.– nat. iranian oil Company, Geol. lab. pub., 7, 165 p.

RAHAGHi, A. (1980): Tertiary faunal Assemblage of Qum–kashan, Sabzewar and Jahrum areas.– national iranian oil Company, Geological laboratories, publication 8, 1–64.

SAMpo, M. (1969): Microfacies and microfossils of the zagros area, Southwestern iran (from pre-permian to Miocene).– Sed. petr. Series, 12, brill., leiden, 102 p.

SCHAUb, H. (1981): nummulites et Assilines de la Téthys paléogène. Taxinomie, phylogénèse et biostratigraphie.– Mém. Suisse paléont., 104, 236 p.

SCHMiDT, G.A. & SHinDEll, D.T. (2003): Atmosphe-ric composition, radiative forcing, and climate change as a consequence of a massive methane release from gas hydrates.– paleoceanography, 18, 1004, 4-1–4-9.

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SilvESTRi, A. (1938):Foraminiferi dell’Eocene della Soma-lia, parte i in paleontologia della Somalia. iv Fossili dell’Eocene.– palaeontolographia italica, XXXii, Suppl. 3, 49–89 (37–77).

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Manuscript received February 28, 2006.Revised manuscript accepted november 24, 2006.

106 Geologia Croatica 59/2

pLatE 1

Somalina praestefaninii n.sp., sample Sh17b, Mibazara Member, Wadi Al nahayan Formation, Gebel Hafit

Figs. 1–10 Microspheric form of Somalina praestefaninii n.sp. (fig. 6 in boUkHARy et al., 2006). Scale = 1 mm.Figs. 11–13 Megalospheric form of Somalina praestefaninii n.sp. Scale = 1 mm.

107Boukhary, Decrouez & El Safori PLAtE 1

108 Geologia Croatica 59/2